By Bruce W. Yardley, W. S. MacKenzie, C. Guilford
This booklet gathers the best ever choice of metamorphic rock pictures. Divided into sections. part One comprises photomicrographs of a large rangeof rock of other chemistries metamorphosed lower than quite a few actual stipulations and in several metamorphic settings. part bargains with textures attribute of metamorphic rocks. In all it comprises over 250 color photos, observed via brief descriptions and dialogue, making this the main visually appealing of the entire significant other volumes.
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Extra resources for Atlas of Metamorphic Rocks and Their Textures
The splay cracks along boundary 7 have more consistent orientations than those along boundary 11. g. Figs 5, 7 and 8). Throughout the Hackberry Canyon exposure of the Navajo Formation, dune boundaries dip Fig. 7. Map of splay cracks along dune boundary 7. Equal-area stereonets (lower hemisphere) of splay crack orientation along dune boundaries 7 and 11. Whereas dune boundaries dip gently to the southeast, splay cracks along these boundaries are more steeply dipping to the northwest. The layer above the dune boundary slips to the northwest, along the dune shallowly to the southeast (Table 1, Figs 5, 7 and 8), whereas splay cracks (both above and below the dune boundaries) dip approximately to the northwest (Figs 5, 7 and 8).
First-order bounding surfaces are planar and extensive surfaces that cross-cut higher-order (smaller-scale) bounding surfaces (Brookfield 1977) and may be overlain by interdune strata (Kocurek 1981). Higher-order bounding surfaces dip relative to the first-order bounding surface and may be non-planar (Brookfield 1977). For the purposes of this study, we are interested in first-order bounding surfaces that are overlain by interdune deposits, because these surfaces may localize deformation. Within this paper first-order bounding surfaces underlying interdune strata are referred to as dune boundaries.
For fold amplitudes of less than 28m, the region below 1765 m does not slip and the shear stresses are not reduced within the region. 5m depth stores shear strain energy by deforming elastically through its thickness. At 28-m fold amplitude, the interface underlying this stiff layer slips and the shear stresses and strains within the layer are reduced. This strain is transferred from the layer as frictional slip, which localizes shear strain along the interfaces. The change in shear strain distribution at fold amplitude higher 45 than 28m influences the pattern of slip and brings the location of maximum slip below the middle of the layer.